From Wikipedia, the free encyclopedia
Jump to: navigation, search
Category Phyllosilicate
(repeating unit)
Strunz classification 09.EG.35
Crystal symmetry Trigonal pyramidal
H-M symbol: (3)
Space group: R 3
Unit cell a = 11.66 Å, c = 28.69 Å; Z = 3
Color Light to medium green
Crystal habit Tabular crystals
Crystal system Trigonal
Cleavage Perfect {0001}
Fracture Micaceous
Tenacity Flexible
Luster Sub-vitreous, resinous, greasy
Streak white
Diaphaneity Translucent
Specific gravity 3.146
Optical properties Uniaxial (-)
Refractive index nω = 1.643 nε = 1.623
Birefringence δ = 0.020
Pleochroism Weak; O = pale green; E = colorless
References [1][2][3]

Zussmanite (K(Fe2+,Mg,Mn)13[AlSi17O42](OH)14) is a hydrated iron-rich silicate mineral. Zussmanite occurs as pale green crystals with perfect cleavage.

Discovery and occurrence[edit]

It was first described in 1960 by Stuart Olof Agrell in the Laytonville quarry, Mendocino County, California. Zussmanite is named in honor of Jack Zussman (born 1924), Head of the University of Manchester’s Department of Geology and co-author of Rock-Forming Minerals. In the Laytonville quarry, Zussmanite occurs in metamorphosed shales, siliceous ironstones and impure limestones of the Franciscan Formation. It is a location of high pressure and low temperatures where blueschist facies metamorphic rocks occur. This is also the locality in which Deerite and Howieite were first discovered. This type of locality also produces micas, which have a similar structure as zussmanite.

The locality in which zussmanite occurs is one of ultra high to high pressure and low temperatures. This Barrovian type of metamorphism is usually distinguished by the P/T range rather than the ranges in pressure and temperatures (Miyashiro et al.,1973). The three principal Barrovian types are low P/T type, medium P/T type, and high P/T type. The high P/T type, referred to as glaucophanic metamorphism, is characterized by the presence of glaucophane and forms glaucophane schists (Miyashiro et al.,1973). Glaucophane schists, commonly referred to as blueschist-facies, result from metamorphism of basaltic rocks and are usually located in folded geosynclinal terranes (Deer, Howie, Zussman et al.,1992). Glaucophane schists are characterized by low temperature (100–250 °C) high pressure (4-9 kbar) metamorphism (Deer, Howie, Zussman et al.,1992). Zussmanite is commonly found with stilpnomelane and quartz, usually forming abundant porphyroblasts up to 1 mm in size, in the newly discovered locality in Southern Central Chile ( Massonne et al., 1998).


The blueschist facies phyllosilicate mineral occurs as a result of subduction of oceanic crustal rocks and oceanic-continental margin sediments along convergent plate boundaries. The ideal formula for zussmanite is KFe13Si17AlO42(OH)14 with possible substitutions of sodium (Na) for potassium (K), in extremely small amounts (Lopes et al.,1969). The possible iron (Fe2+) substitutes are mainly magnesium (Mg) with trace amounts that could include: manganese (Mn), aluminium (Al), iron3+ (Fe3+) and titanium (Ti) (Lopes et al.,1969). Zussmanite was discovered in combination with deerite and howieite, two new minerals discovered in the Franciscan formation, Mendocino County, California. Deerite and howieite have been found at other locations while zussmanite has only been found at this type locality, making it a rare occurring mineral. Experiments have revealed that zussmanite is stable up to 600 °C at pressures between 10 kb and 30 kb and that the end members of zussmanite are orthoferrosilite, biotite and quartz. The example of the reaction is KFe13[AlSi17042](OH)14 (zussmanite) yields 10FeSiO3 (orthoferrosilite) + ½ K2Fe6Si6Al2O20(OH)4 (biotite) + 4SiO2 (quartz) + 6H20 (water) (Dempsey et al.,1981). The manganese analogue of zussmanite, coombsite, has been found in manganese-rich siliceous rocks in the Otago Schist in New Zealand.


The space group and cell of Zussmanite are R*3, ahex 11.66 and chex28.69 Angstroms (Agrell et al., 1965). The structure of Zussmanite contains continuous sheets of rhombohedrally stacked layers of Fe-O octahedral parallel to (0001) (Lopes et al., 1967) and to either side of these are attached (Si,Al)-O tetrahedral in a way to produce a rhombohedral unit cell(Lopes et al.,1969). These layers are linked to one another by Potassium (K) atoms and also by three-member rings of tetrahedra that share oxygens with the six-members; displayed in figure 2 (Lopes et al.,1967). Zussmanite’s structure has a close affinity to that of the trioctahedral micas which have a layer of Fe-O octahedral sandwiched between inward pointing tetrahedral. It differs from the micas because its Si-O ratio is 9:21 which results in a sharing coefficient 1.83, as compared with 2.5 and 1.75 for micas, and 1.2 and 2.0 for framework silicates (Lopes et al.,1969). The Fe-(O,OH) mean distance in the first octahedron is 2.1 Angstroms, the second octahedron is 2.14 Angstroms, and in the third Octahedron is 2.17 Angstroms. The mean distance in the Si-O bonds in Zussmanite are 1.61 Angstroms for the first tetrahedron, 1.61 Angstroms for the second tetrahedron, and 1.65 Angstroms for the third tetrahedron; data given in table I (Lopes et al.,1969). The six-member rings are not directly linked to one another which allows for adjustment by tilting outwards of all tetrahedral, as opposed to many micas where rotations and tilts are used to achieve the larger dimensions of the octahedral layer. The flattening of the octahedral layer perpendicular to the layer is pronounced in Zussmanite due to shared and unshared edges. This flattening could be due to the tendency for shared oxygens to come closer and shields iron (Fe) atoms from other neighboring iron (Fe) atoms.

Physical properties[edit]

Zussmanite occurs in pale green tabular crystals with perfect cleavage. It tends to be uniaxial, weakly pleochroic and a specific gravity of 3.146 (Agrell et al.,1965). Other types of zussmanite found in Laytonville, which are of fine-grained samples are assumed to be late-stage metamorphic products. The perfect cleavage is a result of the continuous sheets of (Fe,Mg)-(O,OH) octahedra parallel to (0001). The optical properties result from virtually pure zussmanite that was separated from thin sections, approximately 200 micrometres thick, under a polarizing microscope by means of a microdrill. The indices of refraction compare well with those determined be Agrell et al.,1965 for the chemically different Zussmanite from the Laytonville quarry (Massonne et al., 1998).


  1. Agrell, S.O.; Bown, M.G.; McKie, D. (1965). "Deerite, howieite and zussmanite, three new minerals from the Franciscan of the Laytonville District, Mendocino County, California". Mineralogical Magazine 50: 278. 
  2. Deer, W.; Howie, R; Zussman, J. (1993). An Introduction to the Rock-Forming Minerals. Pearson Education Limited publishing. 2nd edition.
  3. Dempsey, M.J. (1981) Zussmanite Stability; A Preliminary Study. Progress in Experimental Petrology. Volume 5. Pages 58-60.
  4. Lopes-Vieira, A.; Zussman J. (1967). "The Crystal Structure of the Mineral Zussmanite". Mineralogical Magazine 36 (278): 292–293. doi:10.1180/minmag.1967.036.278.11. 
  5. Lopes-Vieira, A.; Zussman J. (1969). "Further Detail on the Crystal Structure of Zussmanite". Mineralogical Magazine 37 (285): 28–60. 
  6. Massonne, H.-J. (1998). Zussmanite in ferruginous metasediments from Southern Central Chile. Mineralogical Magazine. Volume 62, Issue 6. Pages 869-876.
  7. http://www.mindat.org/photo-82023.html. Photo Copyright at California Institute of Technology.
  8. Miyashiro A.(1973). Metamorphism and metamorphic belts. Allen & Unwin, London, 492 pp.

External links[edit]